Hostname: page-component-6766d58669-nf276 Total loading time: 0 Render date: 2026-05-21T22:49:52.763Z Has data issue: false hasContentIssue false
  • English
  • Français

A decade of in situ cosmogenic 14C in Antarctica

Published online by Cambridge University Press:  27 March 2023

Keir Alexander Nichols Open the ORCID record for Keir Alexander Nichols [Opens in a new window]
Keir Alexander Nichols*
Affiliation:
Imperial College London, London, UK
*
Author for correspondence: Keir Alexander Nichols, E-mail: keir.nichols@imperial.ac.uk
Rights & Permissions [Opens in a new window]

Abstract

Cosmogenic nuclide measurements in glacial deposits extend our knowledge of glacier chronologies beyond the observational record. The short half-life of in situ cosmogenic 14C makes it particularly useful for studying glacier chronologies, as resulting exposure ages are less sensitive to nuclide inheritance when compared with more commonly measured, long-lived nuclides. An increasing number of laboratories using an automated process to extract carbon from quartz has led to in situ 14C measurements in Antarctic samples at an accelerating rate over the past decade, shedding light on deglaciation in Antarctica. In situ 14C has had the greatest impact in the Weddell Sea Embayment, where inferences on the thickness of ice and timing of deglaciation were limited by inheritance in other cosmogenic nuclide systems. Future subglacial measurements of the nuclide hold much potential as they can provide direct evidence of proposed Holocene thinning and subsequent re-thickening of parts of the Antarctic ice sheets.

Keywords

Glacial geologyice chronology/datingpaleoclimate

Information

Type
Letter
Information
Annals of Glaciology , Volume 63 , Issue 87-89 , September 2022 , pp. 67 - 72
Check for updates
Creative Commons
Creative Common License - CCCreative Common License - BY
This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
Copyright
Copyright © The Author(s), 2023. Published by Cambridge University Press on behalf of The International Glaciological Society

Introduction

Cosmogenic nuclides are rare nuclides made in near-surface rocks and minerals by cosmic rays. The concentration of a cosmogenic nuclide in a surface is directly proportional to the time the surface was most recently uncovered by receding ice. As such, measuring cosmogenic nuclide concentrations is a common way of studying glacier chronologies (Schaefer and others, Reference Schaefer2022). By measuring cosmogenic nuclides at different elevations above glaciers, we can constrain both the past thickness and timing and pattern of thinning (Ackert and others, Reference Ackert1999; Stone and others, Reference Stone2003), typically following the Last Glacial Maximum (LGM). These geologic constraints are used to validate the results of numerical ice sheet models investigating deglaciation (e.g., Whitehouse and others, Reference Whitehouse, Bentley and Le Brocq2012; Pittard and others, Reference Pittard, Whitehouse, Bentley and Small2022), informing model parameter selection and ultimately reducing uncertainties when these same models are used to simulate the future response of ice sheets to a changing climate.

Concentrations of cosmogenic nuclides are converted to exposure ages using production rates and, for radioactive nuclides, their half-lives. Most exposure dating studies use 10Be or combine it with 26Al (with half-lives of 1.4 and 0.7 Myr, respectively) (Balco, Reference Balco2011). Exposure dating studies rely on the assumption that concentrations accumulated in a single phase of exposure. Cosmogenic nuclides are predominantly produced in the upper few metres of rock, and we rely on erosion during glaciations to ‘reset’ surfaces. Preserved beneath cold-based (nonerosive) ice, long-lived nuclides like 10Be can persist for multiple glacial-interglacial cycles, breaking the assumption of one period of exposure. Another cosmogenic nuclide, in situ 14C, has a much shorter half-life (5700 ± 30 yr), making concentrations and resulting exposure ages less sensitive to this nuclide ‘inheritance’. The half-life is so short that 14C accumulated prior to the LGM will have decayed away, regardless of how much erosion took place. In situ 14C exposure ages are therefore essentially free of inheritance, providing unambiguous evidence for the timing of glacier thinning or retreat.

Another useful aspect of in situ 14C is the potential to constrain the maximum extent of LGM ice. A balance between production and decay is reached after about 5.5 times the half-life of a radioactive cosmogenic nuclide, at which point a surface is ‘saturated’. This means a surface is saturated with in situ 14C after ≈30 ka of exposure, assuming minimal erosion. When we measure a concentration equivalent to saturation, we know that the sample has been exposed for at least 30 ka, and thus was not covered during the LGM. Hence, surfaces saturated with in situ 14C provide unambiguous evidence for the extent of ice during the LGM. In summary, in situ 14C is useful for studying deglaciation because (i) concentrations are essentially uninfluenced by previous periods of exposure, providing exposure ages that are more likely to reflect the true age of deglaciation when compared with those from long-lived nuclides and (ii) measurements can provide upper constraints on the extent of ice at the LGM, a type of constraint that cannot be provided by measuring long-lived nuclides. Both of these aspects of in situ 14C mean measuring it is particularly useful for benchmarking the results of numerical ice sheet models.

A growing number of laboratories capable of extracting in situ 14C and automation of the extraction process have led to the nuclide being measured at an enhanced rate over the last decade (Fig. 1a). These measurements are advancing our knowledge of the most recent deglaciation in Antarctica, especially where inferences from long-lived nuclides are limited. How in situ 14C is measured, where in Antarctica it has been measured and what these measurements have shown us about deglaciation, are described below. Potential research questions that can be addressed using this nuclide are also outlined, including estimating glacial erosion rates by combining measurements of in situ 14C and 10Be, assessing the outputs of numerical ice sheet models with single measurements of in situ 14C, and investigating and quantifying a proposed Holocene thinning (beneath present) episode with subglacial measurements of in situ 14C. Much of our knowledge of the past of the Antarctic ice sheets is based on periods when the ice sheets were larger than today, such as during the LGM, because evidence for past ice extent is preserved in rock and sediments above, adjacent to and offshore of present ice margins. Knowledge of contracted configurations of the Antarctic ice sheets, gained through subglacial measurements of in situ 14C, is key to understanding the future of the ice sheets given that they are predicted to continue losing mass (DeConto and others, Reference DeConto2021).

Fig. 1.

(a) Cumulative (black) and yearly (grey bars) total in situ 14C measurements from Antarctica (excluding CRONUS A). (b) Sampling locations of all published subaerial in situ 14C measurements from Antarctica, excluding those of CRONUS-A (purple star). WAIS and EAIS are the West and East Antarctic Ice Sheets, respectively. Measurements sourced from the following studies: Antarctic Peninsula (AP), Jeong and others (Reference Jeong2018), Lassiter Coast (LC), Pensacola Mountains (PM) and Shackleton Range (SR), Nichols and others (Reference Nichols and Goehring2019), Ellsworth Mountains (EM), Fogwill and others (Reference Fogwill2014) and Spector and others (Reference Spector, Stone and Goehring2019), Whitmore Mountains (WM), Spector and others (Reference Spector, Stone and Goehring2019), Amundsen Sea Embayment (ASE), Johnson and others (Reference Johnson2017, Reference Johnson2020), Transantarctic Mountains (TAM), Hillebrand and others (Reference Hillebrand2021), northern Victoria Land (NVL), Goehring and others (Reference Goehring, Balco, Todd, Moening-Swanson and Nichols2019b) and Balco and others (Reference Balco, Todd, Goehring, Moening-Swanson and Nichols2019), Prydz Bay, Berg and others (Reference Berg2016) and White and others (Reference White, Fülöp, Bishop, Mackintosh and Cook2011), Queen Maud Land (QML), Akçar and others (Reference Akçar2020). Map made with Quantarctica (Matsuoka and others, Reference Matsuoka, Skoglund and Roth2018).

How is in situ 14C measured?

The utility of in situ 14C exposure dating has long been known (e.g., Lal, Reference Lal1987, Reference Lal1988; Lal and Jull, Reference Lal and Jull2001) but it was not until the 2010s that improved reproducibility, increased reliability in extraction systems and an accompanying reduction in blank levels, helped make measuring it more routine. Building on methods for measuring in situ 14C in extraterrestrial samples (Goel and Kohman, Reference Goel and Kohman1962; Suess and Wänke, Reference Suess and Wänke1962), Lifton and others (Reference Lifton, Jull and Quade2001) developed the methods for extracting carbon from quartz used in laboratories today. While methods differ with laboratory, the key steps are similar: carbon is liberated through the heating of quartz under vacuum, oxidised to form CO2, then purified using liquid nitrogen. Some extraction lines use a tube furnace and fuse quartz in a lithium metaborate flux (Lifton and others, Reference Lifton, Goehring, Wilson, Kubley and Caffee2015; Lamp and others, Reference Lamp2019; Goehring and others, Reference Goehring, Wilson and Nichols2019a), while others use an electron bombardment or resistance furnace to release in situ 14C by diffusion through the crystal lattice (Fülöp and others, Reference Fülöp, Wacker and Dunai2015, Reference Fülöp2019; Lupker and others, Reference Lupker2019). Samples are sent for AMS measurement as CO2 (Hippe and others, Reference Hippe2013; Lupker and others, Reference Lupker2019) or after dilution and graphitisation (e.g., Lifton and others, Reference Lifton, Goehring, Wilson, Kubley and Caffee2015). Isotope ratios are used to determine in situ 14C concentrations following Hippe and Lifton (Reference Hippe and Lifton2014). In situ 14C concentrations, combined with sample density, thickness, elevation, latitude and longitude and topographic shielding, are then used to calculate exposure ages, usually using an online exposure age calculator such as the online calculators formerly known as the CRONUS-Earth online calculators (Balco and others, Reference Balco, Stone, Lifton and Dunai2008).

The rise in the number of studies applying in situ 14C (Fig. 1a) is fuelled by a number of factors, among which most notable are a growing number of extraction lines, automation of extraction, decreasing blank levels and the widespread adoption of data reduction and production rate calibration methods. Most importantly, an increasing number of laboratories are capable of extracting carbon from quartz. Automation of the extraction process has increased sample throughput, particularly at Tulane University (Goehring and others, Reference Goehring, Wilson and Nichols2019a). A gradual reduction in 14C in process blanks has improved the detection limit. Repeat measurements of the in situ 14C concentration of the interlaboratory comparison material CRONUS-A (Jull and others, Reference Jull, Scott and Bierman2015) have been used to characterise the reproducibility of in situ 14C measurements (approximately 6%; Nichols and others, Reference Nichols2019) and calibrate the production rate used by the online exposure age calculators (Balco and others, Reference Balco, Stone, Lifton and Dunai2008) and the Informal Cosmogenic-Nuclide Exposure-age Database (ICE-D, ice-d.org, Balco, Reference Balco2020). Standardisation of data reduction (Hippe and Lifton, Reference Hippe and Lifton2014) and the identification of a source of contamination from a commonly used method of quartz isolation (Nichols and Goehring, Reference Nichols and Goehring2019) have also contributed to the now relatively routine measurement and application of in situ 14C.

Advances based on in situ 14C

Measurements of in situ 14C are reported from all sectors of Antarctica but are focused in the Ross, Weddell and Amundsen sea embayments, with a dearth of measurements in East Antarctica and few on the Antarctic Peninsula (Fig. 1b). Post-LGM exposure ages constrain deglaciation at most sites, and saturated measurements constrain the limit of LGM ice in the Shackleton Range (Nichols and others, Reference Nichols2019), close to the West Antarctic Ice Sheet (WAIS) Divide (Spector and others, Reference Spector, Stone and Goehring2019) and adjacent to Prydz Bay (Berg and others, Reference Berg2016). Samples saturated with in situ 14C are also observed on blue ice moraines in Queen Maud Land (Akçar and others, Reference Akçar2020). CRONUS-A, a sandstone sample sourced from 1679 m asl in Arena Valley in the Dry Valleys, Antarctica (Jull and others, Reference Jull, Scott and Bierman2015; Fig. 1b), is saturated with 14C and has been measured at least 75 times.

The most obvious places to measure in situ 14C for exposure dating studies are those yielding solely or primarily pre-LGM exposure ages from long-lived nuclides, and thus inferences on the extent of LGM ice are limited. This is the case at the Lassiter Coast in the Weddell Sea Embayment (Fig. 1b), where the majority of 10Be exposure ages of deposits, presumably from the LGM or most recent deglaciation, exceed 100 ka (Fig. 2a). Taken at face value, one could infer that ice has not been thicker here for hundreds of thousands of years, certainly not during the LGM. However, in situ 14C measurements made at the same site, with many of the same samples, yield Holocene exposure ages (Fig. 2a), showing that (i) ice was at least 380 m thicker than present at the LGM, (ii) deglaciation occurred relatively rapidly and (iii) this region was covered by cold-based ice that preserved 10Be that accumulated during previous periods of exposure.

Fig. 2.

(a) Exposure ages from the Lassiter Coast (Johnson and others, Reference Johnson, Nichols, Goehring, Balco and Schaefer2019; Nichols and others, Reference Nichols and Goehring2019) sourced from ICE-D using the LSDn scaling method. Error bars show external uncertainties but are often smaller than symbols. (b) Collection site of a bedrock sample (P11-11-4) on the Bowman Peninsula, Lassiter Coast (Johnson and others, Reference Johnson, Nichols, Goehring, Balco and Schaefer2019). This bedrock sample has a 10Be exposure age of 410 ± 30 ka and an in situ 14C exposure age of 7.4 ± 0.6 ka. Photo credit: Joanne Johnson (British Antarctic Survey).

A similar pattern of pre-LGM 10Be exposure ages and post-LGM in situ 14C exposure ages is observed at other sites in the Weddell Sea Embayment. Limited LGM thickening inferred from predominantly pre-LGM 10Be exposure ages in the Shackleton Range (Hein and others, Reference Hein, Fogwill, Sugden and Xu2011) and Pensacola Mountains (Balco and others, Reference Balco2016; Bentley and others, Reference Bentley2017) was used to benchmark ice sheet models for some time (e.g., Whitehouse and others, Reference Whitehouse2017; Kingslake and others, Reference Kingslake2018). These interpretations led to relatively little post-LGM ice volume change in the Weddell Sea Embayment (when compared with previous reconstructions, see Bentley and Anderson (Reference Bentley and Anderson1998)) becoming the predominant reconstruction among the palaeo community (Hillenbrand and others, Reference Hillenbrand2014). Subsequent measurements of in situ 14C yielded post-LGM exposure ages at both locations, showing that, rather than limited thickening, ice was at least 310 and 800 m thicker than present at the LGM (Nichols and others, Reference Nichols2019). Other locations with multiple samples yielding pre-LGM exposure ages from long-lived nuclides and post-LGM in situ 14C exposure ages are the Flower Hills and Meyer Hills in the Ellsworth Mountains (Fogwill and others, Reference Fogwill2014) and the Darwin–Hatherton Glacier System in the Ross Sea Embayment (Hillebrand and others, Reference Hillebrand2021).

In situ 14C can also be useful at sites yielding post-LGM 10Be exposure ages. For example, in the Amundsen Sea Embayment, Johnson and others (Reference Johnson2020) use measurements of in situ 14C to identify a smaller degree of inheritance in their exposure ages. Here, 10Be exposure ages (n = 9) indicate deglaciation happened about 17 ka, while in situ 14C exposure ages (n = 8) show it occurred about 6 ka, a difference of 11 ka, which is significant for establishing an accurate deglacial chronology of the region. Samples with post-LGM 10Be exposure ages and younger in situ 14C exposure ages are also observed at sites in northern Victoria Land (Balco and others, Reference Balco, Todd, Goehring, Moening-Swanson and Nichols2019; Goehring and others, Reference Goehring, Balco, Todd, Moening-Swanson and Nichols2019b), with an additional sample in the Flower Hills (Fogwill and others, Reference Fogwill2014). Evidently, even when 10Be exposure ages at a site postdate the LGM and thus we know the degree of ice thickness change, there could still be a detectable amount of inheritance skewing our understanding of the timing of deglaciation.

Glacier chronologies are constrained solely with in situ 14C measurements (without accompanying long-lived nuclides) at some locations, such as the Whitmore Mountains close to WAIS Divide (Spector and others, Reference Spector, Stone and Goehring2019) and some sites in northern Victoria Land (Goehring and others, Reference Goehring, Balco, Todd, Moening-Swanson and Nichols2019b). Additionally, concordant in situ 14C and 10Be exposure ages are observed at many sites in Antarctica (White and others, Reference White, Fülöp, Bishop, Mackintosh and Cook2011; Balco and others, Reference Balco, Todd, Goehring, Moening-Swanson and Nichols2019; Goehring and others, Reference Goehring, Balco, Todd, Moening-Swanson and Nichols2019b; Hillebrand and others, Reference Hillebrand2021).

Future research priorities

Measuring in situ 14C

While we have learnt much about deglaciation in Antarctica from in situ 14C in recent years, we have also learnt much about measuring the nuclide itself, and some questions remain unanswered. Some studies observe in situ 14C concentrations in excess of theoretical limits (Balco and others, Reference Balco2016; Akçar and others, Reference Akçar2020), while another observes measurement reproducibility lower than that expected from measurement uncertainties alone (Nichols and others, Reference Nichols2019). When sample contamination can be ruled out, mass movement and supraglacial transport could explain elevated concentrations (Balco and others, Reference Balco2016), while unrecognised measurement error could explain the limited reproducibility. Further work dedicated to method development is needed to isolate what is (i) limiting measurement reproducibility and (ii) contributing toward concentrations exceeding theoretical limits. Most studies measure in situ 14C in quartz, but the nuclide is produced in other materials such as calcium carbonate (Handwerger and others, Reference Handwerger, Cerling and Bruhn1999) and olivine (Pigati and others, Reference Pigati, Lifton, Jull and Quade2010). Establishing methods for the extraction of carbon from these materials would expand the number of locations we can study with in situ 14C beyond only those rich in quartz.

Applying in situ 14C

Further exposure dating studies using in situ 14C would be useful in areas unstudied with cosmogenic nuclides or those yielding solely or primarily pre-LGM exposure ages from long-lived nuclides (e.g., Hodgson and others, Reference Hodgson2012). By filling spatial gaps in our knowledge of deglaciation in Antarctica, these measurements of in situ 14C would provide more geologic constraints for the benchmarking of numerical ice sheet models. Additionally, there are a few applications beyond traditional exposure dating yet to be used (or to their full potential) that could improve our knowledge of the history and glaciology of the Antarctic ice sheets.

How much did glaciers erode into bedrock during the Holocene? This question can be answered by combining measurements of in situ 14C and 10Be in recently exposed proglacial bedrock. Making direct measurements of subglacial erosion is complicated by the difficulty of accessing the beds of glaciers. Using cosmogenic nuclides to estimate past erosion rates provides knowledge of glacial processes over a longer period than contemporary point measurements, extending our knowledge of glacial erosion rates beyond the observational record. The relationship between the in situ 14C and 10Be concentration of a proglacial bedrock sample is related to the depth to which a glacier eroded into bedrock in the Holocene, allowing the estimation of Holocene glacial erosion rates (Rand and Goehring, Reference Rand and Goehring2019). Because this method requires proglacial bedrock, it may be limited to smaller glaciers such as those on the Antarctic Peninsula or at high elevations on the continent.

How closely do numerical ice sheet model outputs reflect the timing of both the advance and retreat phases of deglaciation contained in geologic archives? Measurements of in situ 14C, rather than long-lived nuclides, can answer this question. Many numerical ice sheet models are benchmarked against exposure age datasets recording only deglaciation. By assuming samples were saturated prior to LGM burial, individual measurements of in situ 14C can be used to assess the timing of both advance and retreat phases of model outputs (Spector and others, Reference Spector, Stone and Goehring2019), reducing uncertainties when these same models are used to simulate the future of ice sheets. More generally, targeting exposed surfaces high above modern ice elevations could help provide more upper constraints on LGM ice thicknesses to help validate numerical ice sheet model outputs.

To what extent, and where, did parts of the Antarctic ice sheets readvance in the Holocene? This is perhaps the most important question that in situ 14C can answer. A number of studies, both through geologic observations (Siegert and others, Reference Siegert, Ross, Corr, Kingslake and Hindmarsh2013; Wolstencroft and others, Reference Wolstencroft2015; Greenwood and others, Reference Greenwood, Simkins, Halberstadt, Prothro and Anderson2018; King and others, Reference King, Watson and White2022) and modelling (Kingslake and others, Reference Kingslake2018), infer that some parts of the Antarctic ice sheets were smaller than present in the Holocene and subsequently grew to their present configuration. Through measuring carbon in subglacial sediments, two studies (Venturelli and others, Reference Venturelli2020 and Neuhaus and others, Reference Neuhaus2021) report the first direct evidence of a Holocene grounding line readvance in the Ross sector. Further direct evidence for a Holocene readvance can be obtained through in situ 14C measurements in subglacial bedrock, because significant concentrations in subglacial bedrock unambiguously requires Holocene exposure, either complete or through relatively thin ice (Johnson and others, Reference Johnson2022). Constraining the scale of this readvance, both in ice thickness change and geographic extent, could shed light on the processes causing the mass loss and subsequent gain (e.g., ocean forcings, glacioisostatic adjustment), information that can then be used with numerical models to replicate this ice sheet behaviour. Given that current Antarctic ice sheet mass loss is predicted to continue (DeConto and others, Reference DeConto2021), knowing the processes that helped recover ice mass loss in a climate relatively similar to that of today is key to understanding the reversibility of current and future Antarctic ice mass loss. While previous studies have investigated long term changes in the Greenland Ice Sheet by measuring long-lived nuclides in subglacial material (Schaefer and others, Reference Schaefer2016; Christ and others, Reference Christ2021), there are no published subglacial measurements of in situ 14C from beneath any ice sheet. If above background in situ 14C indicative of a Holocene readvance is measured in samples collected from beneath the Antarctic ice sheets, multiple studies will be required to confirm if this ice sheet behaviour is widespread or localised.

Conclusions

To summarise, the cosmogenic nuclide in situ 14C has been measured at an enhanced rate over the last decade, fuelled by the automation of the extraction process and an increasing number of laboratories now capable of extracting it. Measurements of in situ 14C have been used in exposure dating studies to shed light on deglaciation in all sectors of Antarctica, but especially in the Weddell Sea Embayment. Some studies observe in situ 14C concentrations exceeding theoretical limits and also measurement reproducibility lower than expected, which can hopefully be addressed with dedicated work on understanding the extraction process and geomorphic scatter. While there are many locations in Antarctica where traditional in situ 14C exposure dating studies would be useful, there are also a number of other applications of the nuclide that hold much potential, including using subglacial measurements to constrain episodes of thinning and rethickening in the Holocene.

References

Ackert, RP Jr and 6 others (1999) Measurements of past ice sheet elevations in interior west Antarctica. Science 286(5438), 276–280. doi: 10.1126/science.286.5438.27CrossRefGoogle ScholarPubMed
Akçar, N and 6 others (2020) Build-up and chronology of blue ice moraines in Queen Maud Land, Antarctica, Quaternary Science Advances 2(May), 100012. doi: 10.1016/j.qsa.2020.100012CrossRefGoogle Scholar
Balco, G (2011) Contributions and unrealized potential contributions of cosmogenic-nuclide exposure dating to glacier chronology, 1990–2010. Quaternary Science Reviews 30(1–2), 3–27. doi: 10.1016/j.quascirev.2010.11.003Google Scholar
Balco, G and 7 others (2016) Cosmogenic-nuclide exposure ages from the Pensacola Mountains adjacent to the foundation ice stream, Antarctica. American Journal of Science 316, 542–577. doi: 10.2475/06.2016.02Google Scholar
Balco, G (2020) Technical note: a prototype transparent-middle-layer data management and analysis infrastructure for cosmogenic-nuclide exposure dating. Geochronology 2, 169–175. doi: 10.5194/gchron-2020-6CrossRefGoogle Scholar
Balco, G, Stone, JO, Lifton, NA and Dunai, TJ (2008) A complete and easily accessible means of calculating surface exposure ages or erosion rates from 10Be and 26Al measurements. Quaternary Geochronology 3(3), 174–195. doi: 10.1016/j.quageo.2007.12.001CrossRefGoogle Scholar
Balco, G, Todd, C, Goehring, BM, Moening-Swanson, I and Nichols, K (2019) Glacial geology and cosmogenic-nuclide exposure ages from the Tucker Glacier – Whitehall Glacier confluence, northern Victoria Land, Antarctica. American Journal of Science 319(April), 255–286. doi: 10.2475/04.2019.01CrossRefGoogle Scholar
Bentley, MJ and 6 others (2017) Deglacial history of the Pensacola Mountains, Antarctica from glacial geomorphology and cosmogenic nuclide surface exposure dating. Quaternary Science Reviews 158, 58–76. doi: 10.1016/j.quascirev.2016.09.028Google Scholar
Bentley, MJ and Anderson, JB (1998) Glacial and marine geological evidence for the ice sheet configuration in the Weddell Sea–Antarctic Peninsula region during the Last Glacial Maximum. Antarctic Science 10(3), 309–325. doi: 10.1017/s0954102098000388Google Scholar
Berg, S and 6 others (2016) Unglaciated areas in east Antarctica during the last glacial (Marine Isotope Stage 3) – new evidence from Rauer group. Quaternary Science Reviews 153, 1–10. doi: 10.1016/j.quascirev.2016.08.021Google Scholar
Christ, AJ and 17 others (2021) A multimillion-year-old record of Greenland vegetation and glacial history preserved in sediment beneath 1.4 km of ice at Camp Century. Proceedings of the National Academy of Sciences 118(13), 1–8. doi: 10.1073/pnas.2021442118CrossRefGoogle ScholarPubMed
DeConto, RM and 12 others (2021) The Paris climate agreement and future sea-level rise from Antarctica. Nature 593, 83–89. doi: 10.1038/s41586-021-03427-0CrossRefGoogle ScholarPubMed
Fogwill, CJ and 8 others (2014) Drivers of abrupt Holocene shifts in West Antarctic ice stream direction determined from combined ice sheet modelling and geologic signatures. Antarctic Science 26(6), 674–686. doi: 10.1017/S0954102014000613Google Scholar
Fülöp, RH and 7 others (2019) The ANSTO – University of Wollongong in-situ 14C extraction laboratory. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 438(April 2018), 207–213. doi: 10.1016/j.nimb.2018.04.018Google Scholar
Fülöp, RH, Wacker, L and Dunai, TJ (2015) Progress report on a novel in situ 14C extraction scheme at the University of Cologne. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 361, 20–24. doi: 10.1016/j.nimb.2015.02.023Google Scholar
Goehring, BM, Balco, G, Todd, C, Moening-Swanson, I and Nichols, K (2019b) Late-glacial grounding line retreat in the northern Ross Sea, Antarctica. Geology 47(4), 1–4. doi: 10.1130/G45413.1CrossRefGoogle Scholar
Goehring, BM, Wilson, J and Nichols, K (2019a) A fully automated system for the extraction of in situ cosmogenic carbon-14 in the Tulane University cosmogenic nuclide laboratory. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 455, 284–292. doi: 10.1016/j.nimb.2019.02.006CrossRefGoogle Scholar
Goel, PS and Kohman, PK (1962) Cosmogenic carbon-14 in meteorites and terrestrial ages of “Finds” and craters. Science 136(3519), 875–876.Google Scholar
Greenwood, SL, Simkins, LM, Halberstadt, ARW, Prothro, LO and Anderson, JB (2018) Holocene reconfiguration and readvance of the East Antarctic Ice Sheet. Nature Communications 9(1), 1–12. doi: 10.1038/s41467-018-05625-3Google Scholar
Handwerger, DA, Cerling, TE and Bruhn, RL (1999) Cosmogenic 14C in carbonate rocks. Geomorphology 27(1–2), 13–24. doi: 10.1016/S0169-555X(98)00087-7CrossRefGoogle Scholar
Hein, AS, Fogwill, CJ, Sugden, DE and Xu, S (2011) Glacial/interglacial ice-stream stability in the Weddell Sea embayment, Antarctica. Earth and Planetary Science Letters 307(1–2), 211–221. doi: 10.1016/j.epsl.2011.04.037Google Scholar
Hillebrand, TR and 8 others (2021) Holocene thinning of Darwin and Hatherton glaciers, Antarctica, and implications for grounding-line retreat in the Ross Sea. Cryosphere 15(7), 3329–3354. doi: 10.5194/tc-15-3329-2021Google Scholar
Hillenbrand, CD and 14 others (2014) Reconstruction of changes in the Weddell Sea sector of the Antarctic Ice Sheet since the Last Glacial Maximum. Quaternary Science Reviews 100, 111–136. doi: 10.1016/j.quascirev.2013.07.020Google Scholar
Hippe, K and 7 others (2013) An update on in situ cosmogenic 14C analysis at ETH Zürich. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 294, 81–86. doi: 10.1016/j.nimb.2012.06.020Google Scholar
Hippe, K and Lifton, NA (2014) Calculating isotope ratios and nuclide concentrations for in situ cosmogenic 14C analyses. Radiocarbon 56(03), 1167–1174. doi: 10.2458/56.17917Google Scholar
Hodgson, DA and 6 others (2012) Glacial geomorphology and cosmogenic 10Be and 26Al exposure ages in the northern Dufek Massif, Weddell Sea embayment, Antarctica. Antarctic Science 24(4), 377–394. doi: 10.1017/S0954102012000016Google Scholar
Jeong, A and 8 others (2018) Late Quaternary deglacial history across the Larsen B embayment, Antarctica. Quaternary Science Reviews 189, 134–148. doi: 10.1016/j.quascirev.2018.04.011Google Scholar
Johnson, JS and 8 others (2017) The last glaciation of Bear Peninsula, central Amundsen Sea Embayment of Antarctica: constraints on timing and duration revealed by in situ cosmogenic 14C and 10Be dating. Quaternary Science Reviews 178, 77–88. doi: 10.1016/j.quascirev.2017.11.003CrossRefGoogle Scholar
Johnson, JS and 10 others (2020) Deglaciation of Pope Glacier implies widespread early Holocene ice sheet thinning in the Amundsen Sea sector of Antarctica. Earth and Planetary Science Letters 548, 116501. doi: 10.1016/j.epsl.2020.116501CrossRefGoogle Scholar
Johnson, JS and 12 others (2022) Review article: existing and potential evidence for Holocene grounding line retreat and readvance in Antarctica. Cryosphere 16(5), 1543–1562. doi: 10.5194/tc-16-1543-2022CrossRefGoogle Scholar
Johnson, JS, Nichols, KA, Goehring, BM, Balco, G and Schaefer, JM (2019) Abrupt mid-Holocene ice loss in the western Weddell Sea Embayment of Antarctica. Earth and Planetary Science Letters 518, 127–135. doi: 10.1016/j.epsl.2019.05.002Google Scholar
Jull, AJT, Scott, EM and Bierman, P (2015) The CRONUS-Earth inter-comparison for cosmogenic isotope analysis. Quaternary Geochronology 26(1), 3–10. doi: 10.1016/j.quageo.2013.09.003CrossRefGoogle Scholar
King, MA, Watson, CS and White, D (2022) GPS Rates of vertical bedrock motion suggest late holocene ice-sheet readvance in a critical sector of east Antarctica. Geophysical Research Letters 49(4), 1–10. doi: 10.1029/2021GL097232.Google Scholar
Kingslake, J and 9 others (2018) Extensive retreat and re-advance of the West Antarctic Ice Sheet during the Holocene. Nature 558(7710), 430–434. doi: 10.1038/s41586-018-0208-xGoogle Scholar
Lal, D (1987) Cosmogenic nuclides produced in situ in terrestrial solids. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 29(1-2), 238–245.CrossRefGoogle Scholar
Lal, D (1988) In situ produced cosmogenic isotopes in terrestrial rocks. Annual Review of Earth and Planetary Sciences 16, 355–388.Google Scholar
Lal, D and Jull, AJT (2001) In-situ cosmogenic 14C: production and examples of its unique applications in studies of terrestrial and extraterrestrial processes. Radiocarbon 43(2B), 731–742. doi: 10.1017/s0033822200041394Google Scholar
Lamp, JL and 6 others (2019) Update on the cosmogenic in situ 14C laboratory at the Lamont-Doherty Earth Observatory. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 456(April), 1–6. doi: 10.1016/j.nimb.2019.05.064Google Scholar
Lifton, N, Goehring, B, Wilson, J, Kubley, T and Caffee, M (2015) Progress in automated extraction and purification of in situ 14C from quartz: results from the Purdue in situ 14C laboratory. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 361, 381–386. doi: 10.1016/j.nimb.2015.03.028Google Scholar
Lifton, NA, Jull, AJT and Quade, J (2001) A new extraction technique and production rate estimate for in situ cosmogenic 14C in quartz. Geochimica et Cosmochimica Acta 65(12), 1953–1969. doi: 10.1016/S0016-7037(01)00566-XCrossRefGoogle Scholar
Lupker, M and 7 others (2019) In-situ cosmogenic 14C analysis at ETH Zürich: characterization and performance of a new extraction system. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 457(July), 30–36. doi: 10.1016/j.nimb.2019.07.028CrossRefGoogle Scholar
Matsuoka, K, Skoglund, A and Roth, G (2018) Quantarctica [Data set]. Norwegian Polar Institute. doi: 10.21334/npolar.2018.8516e961CrossRefGoogle Scholar
Neuhaus, SU and 6 others (2021) Did Holocene climate changes drive West Antarctic grounding line retreat and readvance? Cryosphere 15(10), 4655–4673. doi: 10.5194/tc-15-4655-2021Google Scholar
Nichols, KA and 5 others (2019) New last glacial Maximum ice thickness constraints for the Weddell Sea Embayment, Antarctica. Cryosphere 13, 2935–2951. doi: 10.5194/tc-13-2935-2019Google Scholar
Nichols, KA and Goehring, BM (2019) Isolation of quartz for cosmogenic in situ 14C analysis. Geochronology 1(1), 43–52. doi: 10.5194/gchron-1-43-2019CrossRefGoogle Scholar
Pigati, JS, Lifton, NA, Jull, AJT and Quade, J (2010) Extraction of in situ cosmogenic 14C from Olivine. Radiocarbon 52(3), 1244–1260. doi: 10.1017/S0033822200046336Google Scholar
Pittard, ML, Whitehouse, PL, Bentley, MJ and Small, D (2022) An ensemble of Antarctic deglacial simulations constrained by geological observations. Quaternary Science Reviews 298, 1–28. doi: 10.1016/j.quascirev.2022.107800CrossRefGoogle Scholar
Rand, C and Goehring, BM (2019) The distribution and magnitude of subglacial erosion on millennial timescales at Engabreen, Norway. Annals of Glaciology 60(80), 73–81. doi: 10.1017/aog.2019.42Google Scholar
Schaefer, JM and 8 others (2016) Greenland was nearly ice-free for extended periods during the Pleistocene. Nature 540(7632), 252–255. doi: 10.1038/nature20146Google Scholar
Schaefer, JM and 6 others (2022) Cosmogenic nuclide techniques. Nature Reviews Methods Primers 2(1), 1–22. doi: 10.1038/s43586-022-00096-9CrossRefGoogle Scholar
Siegert, M, Ross, N, Corr, H, Kingslake, J and Hindmarsh, R (2013) Late Holocene ice-flow reconfiguration in the Weddell Sea sector of West Antarctica. Quaternary Science Reviews 78, 98–107. doi: 10.1016/j.quascirev.2013.08.003Google Scholar
Spector, P, Stone, J and Goehring, B (2019) Thickness of the divide and flank of the West Antarctic Ice Sheet through the last deglaciation. Cryosphere 13(11), 3061–3075. doi: 10.5194/tc-13-3061-2019Google Scholar
Stone, JO and 6 others (2003) Holocene deglaciation of Marie Byrd Land, West Antarctica. Science 299(5603), 99–102. doi: 10.1126/science.1077998Google Scholar
Suess, HE and Wänke, H (1962) Radiocarbon content and terrestrial age of twelve stony meteorites and one iron meteorite. Geochimica et Cosmochimica Acta 26, 475–480.Google Scholar
Venturelli, RA and 9 others (2020) Mid-Holocene grounding line retreat and readvance at Whillans Ice Stream, West Antarctica. Geophysical Research Letters 47(15), 0–2. doi: 10.1029/2020GL088476Google Scholar
White, D, Fülöp, RH, Bishop, P, Mackintosh, A and Cook, G (2011) Can in-situ cosmogenic 14C be used to assess the influence of clast recycling on exposure dating of ice retreat in Antarctica? Quaternary Geochronology 6(3–4), 289–294. doi: 10.1016/j.quageo.2011.03.004Google Scholar
Whitehouse, PL and 5 others (2017) Controls on last glacial maximum ice extent in the Weddell Sea embayment, Antarctica. Journal of Geophysical Research Earth Surface 122, 371–397. doi: 10.1002/2016JF004121Google Scholar
Whitehouse, PL, Bentley, MJ and Le Brocq, AM (2012) A deglacial model for Antarctica: geological constraints and glaciological modelling as a basis for a new model of Antarctic glacial isostatic adjustment. Quaternary Science Reviews 32, 1–24. doi: 10.1016/j.quascirev.2011.11.016Google Scholar
Wolstencroft, M and 12 others (2015) Uplift rates from a new high-density GPS network in Palmer Land indicate significant late Holocene ice loss in the southwestern Weddell Sea. Geophysical Journal International 203(1), 737–754. doi: 10.1093/gji/ggv327Google Scholar
Figure 0

Fig. 1. (a) Cumulative (black) and yearly (grey bars) total in situ 14C measurements from Antarctica (excluding CRONUS A). (b) Sampling locations of all published subaerial in situ 14C measurements from Antarctica, excluding those of CRONUS-A (purple star). WAIS and EAIS are the West and East Antarctic Ice Sheets, respectively. Measurements sourced from the following studies: Antarctic Peninsula (AP), Jeong and others (2018), Lassiter Coast (LC), Pensacola Mountains (PM) and Shackleton Range (SR), Nichols and others (2019), Ellsworth Mountains (EM), Fogwill and others (2014) and Spector and others (2019), Whitmore Mountains (WM), Spector and others (2019), Amundsen Sea Embayment (ASE), Johnson and others (2017, 2020), Transantarctic Mountains (TAM), Hillebrand and others (2021), northern Victoria Land (NVL), Goehring and others (2019b) and Balco and others (2019), Prydz Bay, Berg and others (2016) and White and others (2011), Queen Maud Land (QML), Akçar and others (2020). Map made with Quantarctica (Matsuoka and others, 2018).

Figure 1

Fig. 2. (a) Exposure ages from the Lassiter Coast (Johnson and others, 2019; Nichols and others, 2019) sourced from ICE-D using the LSDn scaling method. Error bars show external uncertainties but are often smaller than symbols. (b) Collection site of a bedrock sample (P11-11-4) on the Bowman Peninsula, Lassiter Coast (Johnson and others, 2019). This bedrock sample has a 10Be exposure age of 410 ± 30 ka and an in situ 14C exposure age of 7.4 ± 0.6 ka. Photo credit: Joanne Johnson (British Antarctic Survey).